Earth:Hatepe eruption

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Short description: Major eruption of Taupō volcano
Hatepe eruption
VolcanoLake Taupō
DateAbout 230 CE
TypePhreatomagmatic, ultra-Plinian
LocationLake Taupō, North Island, New Zealand
[ ⚑ ] : 38°49′S 175°55′E / 38.817°S 175.917°E / -38.817; 175.917
VEI7
ImpactDevastated vegetation in region, expanded Lake Taupō, flooded the Waikato River
Lake taupo landsat & volcanic features.jpg
The Hatepe eruption's main vents (three of the vents in red) ran parallel to Lake Taupō's current southeastern shore. Present active geothermal systems are in light blue.

The Hatepe eruption, named for the Hatepe Plinian pumice tephra layer,[1] sometimes referred to as the Taupō eruption or Horomatangi Reef Unit Y eruption, is dated to 232 CE ± 10[2] and was Taupō Volcano's most recent major eruption. It is thought to be New Zealand's largest eruption within the last 20,000 years. The eruption ejected some 45–105 km3 (11–25 cu mi) of bulk tephra,[3] of which just over 30 km3 (7.2 cu mi) was ejected in approximately 6–7 minutes.[4] This makes it one of the largest eruptions in the last 5,000 years, comparable to the Minoan eruption in the 2nd millennium BCE, the 946 eruption of Paektu Mountain, the 1257 eruption of Mount Samalas, and the 1815 eruption of Mount Tambora.

Stages of the eruption

Hatepe eruption
Hatepe eruption impact on the North Island of a 10 cm ash deposit (white shading) and ignimbrite from pyroclastic flow (yellow shading). The collapse caldera is in light red. It is superimposed on present day New Zealand.

The eruption went through several stages, with six distinct marker horizons identified. Despite the uniform composition of the erupted magma, a wide variety of eruptive styles were displayed, including weak phreatomagmatism, Plinian eruptions, and a huge pyroclastic flow. Rhyolitic lava domes were extruded some years or decades later, forming the Horomatangi Reefs and Waitahanui Bank.[5] Most of the stages only affected the immediate surrounds of the caldera and regions to its east due to prevailing wind patterns.[6] The main extremely violent pyroclastic flow travelled at close to the speed of sound and devastated the surrounding area, climbing over 1,500 m (4,900 ft) to overtop the nearby Kaimanawa Ranges and Mount Tongariro, and covering the land within 80 km (50 mi) with ignimbrite. There is evidence that it occurred on an autumn afternoon and its energy release was about 150 megatons of TNT equivalent.[6] The eruption column penetrated the stratosphere as revealed by deposits in ice core samples in Greenland and Antarctica.[7] As New Zealand was not settled by the Māori until more than 1,000 years later, the area had no known human inhabitants when the eruption occurred. Tsunami deposits of the same age have been found on the central New Zealand coast, evidence that the eruption caused local tsunamis, but much more widespread waves may have been generated (like those observed after the 1883 Krakatoa eruption).[8] The stages as reclassified from 2003 are:[6]

Hatepe eruption stages
Stage Deposit Type Volume Timing
1 unit Y1 phreatomagmatic fine ash 0.05 km3 (0.012 cu mi) hours
2 unit Y2 mainly magmatic dry ash 2.5 km3 (0.60 cu mi)
3 unit Y3 mainly phreatoplinian ash but interrupted by dry magmatic ash 1.9 km3 (0.46 cu mi) up to tens of hours with towards end heavy rain
4 unit Y4 Rotongaio fine phreatoplinian ash 1.1 km3 (0.26 cu mi)
5 unit Y5a Dry vesicular pumice and ash 7.7 km3 (1.8 cu mi) up to 17 hours
unit Y5b Dry pyroclastic flow 1.5 km3 (0.36 cu mi) collapse of 5a eruptive column
6 unit Y6 Taupō ignimbrite 30 km3 (7.2 cu mi) no more than 15 minutes
7 Horomatangi Reefs and Waitahanui Bank rhyolite lava domes 0.28 km3 (0.067 cu mi) up to decades after

After

<mapframe zoom="9" text="Temporary maximum lake areas after the 232 ± 10 CE Hatepe eruption (dark blue shading). Two temporary Lake Reporoa's were created transiently, the larger first, and the second later smaller and very transient, when the dam at the present Lake Taupō outlet failed." align="left" height="370" latitude="-38.67" longitude="176.05" width="260">{{Wikipedia:Map data/Reporoa Caldera}}</mapframe> It is estimated that it might have taken as much as 30 years to refill the emptied lake in the caldera.[6] There were massive changes in the landscape for 40 km (25 mi) around with all life sterilised and prior landforms evened out, with beyond the ignimbrite sheet likely forest fires and ash associated die back especially to the west.[6] The Waikato River had been blocked by ignimbrite deposits with the lowest being at Orakei Korako and the temporary lake that was formed over perhaps 2 to 3 years after the eruption in the older Reporoa Caldera had an area of about 90 km2 (35 sq mi) and a volume of about 2.5 km3 (0.60 cu mi).[9]:109 This broke through in a massive flood with peak flow believed to be 17,000 m3/s, over 100 times the current river maximum flood flow.[6]

In due course the Hatepe eruption further expanded the lake that had formed after the much larger Oruanui eruption around 26,500 years ago. The previous outlet was blocked, raising the lake 35 meters above its present level until it broke out after about 20 years in a huge flood.[6] Over 20 km3 (4.8 cu mi) of water[10]:327 escaped down river in less than 4 weeks, with peak discharge of the order of 30,000 m3/s so flowing for more than a week at roughly 200 times the Waikato River's current rate.[6]

Following the eruption rhyolitic lava domes were extruded, these smaller eruptions of unknown total size also created large pumice rafts that were later discovered deposited on the lake shoreline.[11] The volcano continues to be classified as active with periods of volcanic unrest.[2]

Dating the eruption

Early radiocarbon dating effort on 22 selected carbonized samples yielded an uncalibrated average date of 1,819 ± 17 years BP (131 CE ± 17).[12] Research by Colin J. N. Wilson and others remarked that ongoing calibration pushes the radiocarbon result to a more recent date, and they proposed 186 CE as the exact year of eruption based on ancient Chinese and Roman records of unusual atmospheric phenomena in about this year.[13]

In an effort led by R.S.J. Sparks and others to investigate interhemispheric calibration offset in 1995, the team analyzed the uncalibrated ages of tree rings of a single tree killed in Taupo eruption, cross-matched the uncalibrated tree ring chronology to Northern Hemisphere calibration curve, and extrapolated the calibrated tree ring dates to obtain the outermost ring date of 232 CE ± 15, i.e. the last moment the tree was alive.[14]

In 2012, to circumvent interhemispheric calibration offset, the uncalibrated dates of tree rings of a single tree killed in Taupo eruption were wiggle-matched to New Zealand-derived calibration data set to obtain the currently most precise eruption date of 232 CE ± 8 (95.4% confidence).[15] This date is statistically indistinguishable from that of 1995 study and is the currently accepted date. It is suggested that the presence of magmatic carbon in pre-eruption groundwaters may have contaminated radiocarbon ages.[16] However, rhyolitic shards derived from the Taupo eruption have been identified in the Roosevelt Island ice core and are independently dated to 230 CE ± 19, thus firmly refuting propositions of a potential age bias.[17]

Post-eruption soil deficiencies

The tephra soils associated with the eruption were deficient in several essential minerals, with cobalt deficiency being the cause of bush sickness in animals that precluded productive livestock farming until this issue was identified and addressed. This identification by New Zealand government scientists in 1934 was probably the most significant single advance in New Zealand agriculture ever,[18] but was not able to be fully exploited until the 1950s with the deployment of cobalt-ion-containing superphosphate fertiliser from aircraft.

See also

References

  1. ↑ Talbot, J. P.; Self, S.; Wilson, C. J. N. (1994). "Dilute gravity current and rain-flushed ash deposits in the 1.8 ka Hatepe Plinian deposit, Taupo, New Zealand". Bulletin of Volcanology 56 (6–7): 538–551. doi:10.1007/BF00302834. Bibcode: 1994BVol...56..538T. 
  2. ↑ 2.0 2.1 Illsley-Kemp, Finnigan; Barker, Simon J.; Wilson, Colin J. N.; Chamberlain, Calum J.; Hreinsdóttir, Sigrún; Ellis, Susan; Hamling, Ian J.; Savage, Martha K. et al. (1 June 2021). "Volcanic Unrest at Taupō Volcano in 2019: Causes, Mechanisms and Implications". Geochemistry, Geophysics, Geosystems 22 (6): 1–27. doi:10.1029/2021GC009803. Bibcode: 2021GGG....2209803I. 
  3. ↑ Sutton, Andrew N.; Blake, Stephen; Wilson, Colin J. N. (1995-10-01). "An outline geochemistry of rhyolite eruptives from Taupo volcanic centre, New Zealand" (in en). Journal of Volcanology and Geothermal Research. Taupo Volcanic Zone, New Zealand 68 (1): 153–175. doi:10.1016/0377-0273(95)00011-I. ISSN 0377-0273. Bibcode: 1995JVGR...68..153S. https://dx.doi.org/10.1016/0377-0273%2895%2900011-I. 
  4. ↑ Wilson, CJN (1985-06-28). "The Taupo eruption, New Zealand. II. The Taupo Ignimbrite" (in en). Philosophical Transactions of the Royal Society of London. Series A, Mathematical and Physical Sciences 314 (1529): 229–310. doi:10.1098/rsta.1985.0020. ISSN 0080-4614. Bibcode: 1985RSPTA.314..229W. https://royalsocietypublishing.org/doi/10.1098/rsta.1985.0020. 
  5. ↑ Houghton, B.F. (2007). Field Guide—Taupo Volcanic Zone. .
  6. ↑ 6.0 6.1 6.2 6.3 6.4 6.5 6.6 6.7 Lowe, David J; Pittari, Adrian (2021). "The Taupō eruption sequence of AD 232±10 in Aotearoa New Zealand: A retrospection (ニュージーランド・タウポ火山における 西暦 232±10 年噴火の推移)". Journal of Geography (Chigaku Zasshi 地学雑誌) 130 (1): 117–41. doi:10.5026/jgeography.130.117. ISSN 1884-0884. https://www.jstage.jst.go.jp/article/jgeography/130/1/130_130.117/_article/-char/en/. 
  7. ↑ Winstrup, Mai; Vallelonga, Paul; Kjær, Helle A.; Fudge, Tyler J.; Lee, James E.; Riis, Marie H.; Edwards, Ross; Bertler, Nancy A. N. et al. (2019-04-10). "A 2700-year annual timescale and accumulation history for an ice core from Roosevelt Island, West Antarctica" (in English). Climate of the Past 15 (2): 751–779. doi:10.5194/cp-15-751-2019. ISSN 1814-9324. Bibcode: 2019CliPa..15..751W. https://cp.copernicus.org/articles/15/751/2019/. 
  8. ↑ Lowe, D. J., D.J.; de Lange, W. P. (2000). "Volcano-meteorological tsunamis, the c. 200 CE Taupo eruption (New Zealand) and the possibility of a global tsunami". The Holocene 10 (3): 401–407. doi:10.1191/095968300670392643. 
  9. ↑ Manville, V (2001-04-18). Sedimentology and history of Lake Reporoa: an ephemeral supra‐ignimbrite lake, Taupo Volcanic Zone, New Zealand in Volcaniclastic sedimentation in lacustrine settings. Wiley. pp. 109–40. ISBN 1444304267. 
  10. ↑ Manville, V.; Segschneider, B.; Newton, E.; White, J.D.L.; Houghton, B.F.; Wilson, C.J.N. (2009). "Environmental impact of the 1.8 ka Taupo eruption, New Zealand: Landscape responses to a large-scale explosive rhyolite eruption". Sedimentary Geology 220 (3–4): 318–336. doi:10.1016/j.sedgeo.2009.04.017. 
  11. ↑ von Lichtan, I.J.; White, J.D.L.; Manville, V.; Ohneiser, C. (2016). "Giant rafted pumice blocks from the most recent eruption of Taupo volcano, New Zealand: Insights from palaeomagnetic and textural data". Journal of Volcanology and Geothermal Research 318: 73–88. doi:10.1016/j.jvolgeores.2016.04.003. Bibcode: 2016JVGR..318...73V. https://www.sciencedirect.com/science/article/pii/S037702731630035X. 
  12. ↑ Healy, J; Vucetich, CG; Pullar, WA (1964). Stratigraphy and chronology of late Quaternary volcanic ash in Taupo, Rotorua, and Gisborne districts. New Zealand Department of Scientific and Industrial Research, Wellington. 
  13. ↑ Wilson, C. J. N.; Ambraseys, N. N.; Bradley, J.; Walker, G. P. L. (1980). "A new date for the Taupo eruption, New Zealand". Nature 288 (5788): 252–253. doi:10.1038/288252a0. Bibcode: 1980Natur.288..252W. 
  14. ↑ Sparks, R. J.; Melhuish, W. H.; McKee, J. W. A.; Ogden, J.; Palmer, J. G. (1995). "14C calibration in the Southern Hemisphere and the date of the last Taupo eruption: evidence from tree-ring sequences". Radiocarbon 37 (2): 155–163. doi:10.1017/S0033822200030599. Bibcode: 1995Radcb..37..155S. 
  15. ↑ Hogg, Alan; Lowe, David J.; Palmer, Jonathan; Boswijk, Gretel; Ramsey, Christopher Bronk (2012). "Revised calendar date for the Taupo eruption derived by 14 C wiggle-matching using a New Zealand kauri 14 C calibration data set" (in en). The Holocene 22 (4): 439–449. doi:10.1177/0959683611425551. ISSN 0959-6836. Bibcode: 2012Holoc..22..439H. http://journals.sagepub.com/doi/10.1177/0959683611425551. 
  16. ↑ Kennedy, Ben; Duffy, Brendan; Holdaway, Richard N. (2018-10-05). "Evidence for magmatic carbon bias in 14 C dating of the Taupo and other major eruptions" (in en). Nature Communications 9 (1): 4110. doi:10.1038/s41467-018-06357-0. ISSN 2041-1723. PMID 30291227. Bibcode: 2018NatCo...9.4110H. 
  17. ↑ Piva, Stephen B.; Barker, Simon J.; Iverson, Nels A.; Winton, V. Holly L.; Bertler, Nancy A. N.; Sigl, Michael; Wilson, Colin J. N.; Dunbar, Nelia W. et al. (2023-10-09). "Volcanic glass from the 1.8 ka Taupō eruption (New Zealand) detected in Antarctic ice at ~ 230 CE" (in en). Scientific Reports 13 (1): 16720. doi:10.1038/s41598-023-42602-3. ISSN 2045-2322. https://www.nature.com/articles/s41598-023-42602-3. 
  18. ↑ Lowe, D. J.; Balks, M. R. (2019). "Introduction to Tephra-Derived Soils and Farming, Waikato-Bay of Plenty, North Island, New Zealand". https://researchcommons.waikato.ac.nz/bitstream/handle/10289/12297/Lowe%20and%20Balks%202019%20Intro%20to%20tephra-derived%20soils%20and%20farming%2c%20NZ_final.pdf. 

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